3.1. Paleomagnetic Results
Sedimentary samples were demagnetized generally up to 20 mT (for details see Table S2) which removed the viscous remanent magnetization component causing change in the direction of remanent magnetization during such demagnetization for most of the samples. Intensity of the natural remanent magnetization (NRM) of the samples varies between 8.5-34.1e-3 A/m. Median destructive field (MDF) values where samples lost half of its magnetization range between 5-8 mT for the samples. NRM intensity and MDF values of the samples are shown in supplementary figures (Table S3). Maximum angular deviation (MAD) values for Matuyama and Brunhes sections are between 0.3o-5.4o(Figure 5). These values for transition section are between 0.7o-5.3o which is relatively reliable for detection of the migration of the paleomagnetic vector from a reversed to normal polarity (Figure 5). Comparisons of MAD values with previous studies (Okada et al., 2017; Sagnotti et al., 2014) shows the relative magnitude of fluctuations.
In this study, paleomagnetic data showed inclination values changing by approximately 90o when measuring the sediment from 12.8 to 7.1 cm depth (Figure 6). This revealed the transition nature of the Matuyama-Brunhes magnetic reversal in Za Hajovnou cave. Below this depth, there is a Matuyama section which has inclination fluctuations between -6.3o-88.7o (Figure 6). Inclination angle changes between 33o-65.9o for Brunhes section above transition (Figure 6). Also, transition from reversed to normal polarity can be seen in declination data with similar depth (Figure 6). Despite the fluctuations, magnetic intensity values which can depend on the concentration variation of magnetic carriers of every individual sample, were decreasing for the Matuyama section from the bottom to the transition (Figure 6). After the transition from reversed to normal polarity, these values kept increasing which can be seen in Brunhes section between 7.1-0 cm depth (Figure 6). Figure 6 shows the data in comparison with other studies that consisted of various sediment types and locations around the world. Depth of the data sets was normalized considering the transition zone amd differences of sedimentation rate for each study and is not given in Figure 5, 6. Even though, there are some differencies in absolute values, comparisons of this data set with other studies showed that fluctuations and frequency of fluctuations in our data is consistent with other data sets and serves as a supporting argument for Matuyama-Brunhes magnetic reversal in Za Hajovnou cave (Figure 6).